1 ALBANY-FRASER PROVINCE SYNTHESIS

Compiled by Anthony Budd

1.1 ExecutiveSummary -Geology

The Albany-Fraser province extends along the southern and southwestern margin ofthe Yilgarn Craton. It consists mainly of orthogneiss and granite but also includes largesheets of metagabbro (including the Fraser Complex), remnants of mafic dykes andwidespread metasedimentary rocks. The orthogneisses are derived from LateArchaean and Palaeo- and Mesoproterozoic granitic rocks that were deformed andmetamorphosed during Mesoproterozoic orogenic activity.

The province is composed of Archaean and Proterozoic rocks. Proterozoic intrusiveactivity was accompanied by metamorphism and deformation, and occurred in at leasttwo events. The Biranup Supersuite probably intruded at around 1700 - 1600 Ma, andis mostly composed of heterogeneous orthogneiss. The Nornalup Supersuite appearsto include granites intruded at two ages, approximately 1300 Ma and 1190 Ma. It isdominated by heterogeneous ortho- and paragneisses. There is insufficient detailedinformation to divide the Nornalup Supersuite into two suites as is indicated by thesetwo distinct ages.

Nelson et al. (1995) present a summary of the geological history of the Esperanceregion (eastern part of the Albany-Fraser province). Widespread granite emplacementin the Yilgarn Craton occurred at 2620 Ma, followed by emplacement of granitic rocksin the Albany-Fraser province at 1700-1600 Ma. Arenaceous sediments weredeposited at < ca 1560 Ma. Widespread intrusion of gabbro (Fraser Complex) andgranite into thickened crust at a high metamorphic grade occurred between 1300-1280Ma. Widespread granites were intruded into the southeastern part of the orogenbetween 1190-1130 Ma.

Geochronological studies in the western part of the province have not found anyevidence of the ca 1700-1600 Ma granitic rocks. The post-1300 Ma geologicalhistories of both eastern and western parts of the Albany-Fraser province appear to bebroadly similar.

Granites of both the Biranup and Nornalup Supersuites show similar geochemicaltrends. Analyses of the Nornalup Supersuite include mafic enclaves (Clarke 1995).The granites show little alkali alteration, have a spread of Th/U ratios, and are mostlyreduced, becoming oxidised in the most felsic samples. They are metaluminous, haveincreasing K/Rb (showing that the granites are not K-feldspar-fractionated), and onlythe most felsic samples show any increase in Rb/Sr. Compositions range from tonaliteto granite, and all samples are Sr-depleted, Y-undepleted. Some samples showmoderately high HFSE.

1.2 ExecutiveSummary -MetallogenicPotential

These granites are restite-dominated, as shown by the lack of fractionation and thepresence of mafic enclaves in granites of the Nornalup Supersuite. None of theProterozoic granites of the Albany-Fraser province have any significant metallogenicpotential.

1.3 Future Work Further granite geochemistry, petrology and dating will undoubtedly refine thesubdivision of the granites in this Block, and will possibly alter the understanding oftheir metallogenic potential. This is not a high priority given the lack of fractionationand restitic nature of the granites.

1.4 Methods Information Sources: The geochronological framework of the Albany-Fraser province is nowquite well constrained, with SHRIMP dating carried out on granites of all ages (Black et al.1992; Clark 1995; Nelson et al. 1995; Nelson 1995), however the tectonic framework is stilldebated. There are difficulties in relating dated rocks back to the 1:250 000 geological map

© Geoscience Australia 2001 Albany-Fraser Province 1.1

sheets used as a base for this project’s GIS. In some instances, a single map unit has two verydifferent age determinations, meaning that it is difficult to assign all polygons with the one mapsymbol to one Supersuite. For this reason, and because of limited geochemical data, theSupersuites to which some map units have been assigned here will possibly be changed withfurther work.

Geochemical samples are mostly from Curtin University Honours theses and Nelson et al(1995). References to other literature used are given below. 1:250 000 geological maps andcommentaries were also used. Much of the work carried out in the Albany-Fraser province hasbeen aimed at understanding the tectonic setting (Nelson et al. 1995; Myers and Barley 1992;Myers 1990). As part of this, mafic xenolith-bearing granites are likely to have been over-represented in the sample group, and samples of the most felsic endmembers may be under-represented.

Classification of Granites: In this synthesis, the granites were tentatively grouped using onlylimited geochemistry, brief literature articles, good geochronology coverage, and informationfrom regional-scale mapping (published 1:250 000 mapsheets).

Host Rocks: The metasediments which the granites are presumed to intrude are not welldescribed in the literature; the data available for this are limited, and possibly incomplete.

Related Mineralisation: None of Proterozoic age.

1.5 References Black, L.P., Harris, L.B. and Delor, C.P. 1992. Reworking of Archaean and Early Proterozoiccomponents during a progressive, Middle Proterozoic tectonothermal event in the AlbanyMobile Belt, Western Australia, Precambrian Research, 59, 95-123.

Blockley, J.G. and Myers, J.S. 1990. Proterozoic rocks of the Western Australian shield -geology and mineralisation, in Hughes, F.E. (Ed.), Geology of the Mineral Deposits ofAustralia and Papua New Guinea, The Australian Institute of Mining and Metallurgy:Melbourne, pp 607-615.

Clark, W.C. 1995. Granite petrogenesis, metamorphism and geochronology of the WesternAlbany-Fraser Orogen, Albany, Western Australia, BSc (Honours) thesis, Curtin University ofTechnology, Perth, WA - unpublished.

Myers, J.S. 1990. Albany-Fraser Orogen, in Geology and Mineral Resources of WesternAustralia: Western Australia Geological Survey, Memoir 3, pp 255-263.

Myers, J.S. 1993. Precambrian history of the West Australian Craton and adjacent orogenies,Annual Review of Earth and Planetary Science, 21, 453-485.

Myers, J.S. and Barley, M.E. 1992. Proterozoic tectonic framework and metal deposits ofsouthwestern Australia, Precambrian Research, 58, 345-354.

Nelson, D.R. 1995. Compilation of SHRIMP U-Pb zircon geochronology data, 1994,Geological Survey of Western Australia, Record 1995/3.

Nelson, D.R., Myers, J.S. and Nutman, A.P. 1995. Chronology and evolution of the MiddleProterozoic Albany-Fraser Orogen, Western Australia, Australian Journal of Earth Sciences,42, 481-495.

1.6 Table 1.1

Chpt #

Grouping

(Type)Age(Ma)

Potential Confid Level

PlutonCu Au Pb/Zn Sn Mo/W

2Biranup

(Kalkadoon)1700 Low Low Low Low Low 110 Undivided

3Nornalup

(Kalkadoon)

1300 -1180

Low Low Low Low Low 110 Undivided

© Geoscience Australia 2001 Albany-Fraser Province 1.2

ALBANY-FRASER PROVINCE SYNTHESIS

2 BIRANUP SUPERSUITE

2.1 Timing 1700 - 1600 Ma

2.2 IndividualAges

Primary Ages:

1. Hornblende- biotite gra no di orite gneiss, Da lyup Creek1692 ± 22 Ma, SHRIMP

2. Biotite- hornblende mon zo gran ite gneiss, Lake Gi dong head land1671 ± 16 Ma, SHRIMP

3. Biotite- hornblende gra no dio rite gneiss, Lake Gi dong head land1634 ± 26 Ma, SHRIMP

4. Garnet- biotite mon zo gran ite gneiss, Ten Mile Rocks1670 ± 15 Ma, SHRIMP

5. Horn blende sye no gran ite gneiss, Mount An drew1695 ± 16 Ma, SHRIMP)

Source: Nel son 1995.

The above samples correspond to the following mapunit symbols on the 1:250 000 geologicalmap series:

1. pCn - Esperance; 2, 3. ^mm? - Ravensthorpe; 4,5. ^a - Norseman.

2.3 RegionalSetting

The Biranup Complex occurs as a belt forming the northwestern part of the Albany-Fraser province (Myers 1990). It consists of quartzofeldspathic gneisses, mainlyderived from granitoid rocks, interlayered with smaller amounts of metasedimentaryrocks and metagabbro. The rocks are intensely deformed, and primary layering istransposed. Metamorphism outlasted deformation, and the rocks recrystallised withgranoblastic textures. The granitoid rocks of this Complex have been grouped as theBiranup Supersuite in this report.

2.4 Summary With the limited available data, these intrusives are seen to be unfractionated, and haveno textural evidence for the exsolution of a fluid phase.

2.5 Potential Although extensive, these granites are not considered to have any significantmineralisation potential.

Cu: LowAu: LowPb/Zn: LowSn: LowMo/W: LowCon fi dence level: 110

2.6 DescriptiveData

Location: Eastern part of the Albany province, extending from near the coast inland in anortheasterly direction.

Dimensions and area: Crops out over a length of ~400 km elongated in a northeasterlydirection, and has a width of ~100 km. It has a mapped outcrop area of ~9,600 km2.

2.7 Intrusives Component plutons: Below is a table of granites as they appear on the 1:250 000 geologicalmap series. Some of the granites have been informally named, but these names have not beenused in this report, as it is easier to make spatial reference back to the published maps by usingmapsymbols. Note that these are the mapsymbols used on the published maps; the symbols

© Geoscience Australia 2001 Albany-Fraser Province 2.1

used in this project’s GIS are slightly different in some cases in order to differentiate those units. Where different symbols have been used, they are noted in the units’ mineralogical descriptions below.

SYMBOL DESCRIPTION MAPS

^a Migmatite - granitic gneiss permeated by granitic material Norseman

^ab Gt-bi-qtz-feld augen gneiss - porphyritic metagranite? Norseman

^ac Granodiorite - porphyritic; garnetiferous, c-g, sheared Norseman

^ag Granite - leucocratic, equigranular Norseman

^b Gt-bi-qtz-feld gneiss containing feldspar augen Zanthus

pCg Granite and gneiss - undifferentiated Zanthus

pCm Mixed granites Zanthus

pCn Gneiss - banded, gt-bi gneiss and varying granitic rocks Esperance

^g Granitic gneiss; strongly foliated monzogranite to granodiorite Cundeelee

^l Granite with potassium feldspar phenocrysts Zanthus

^m Migmatite - leucocratic granite and gneisses Balladonia

^m Banded qtz-feld-bi-gt gneiss and migmatite Cundeelee

^mm Migmatite with layered structure Ravensthorpe

^y Equigranular leucocratic granite Zanthus

Form: Domes and sheets.

Metamorphism and Deformation: These granites are strongly deformed in places. They havebeen overprinted during deformation related to the intrusion of the Nornalup Supersuite.

Dominant intrusive rock types: Granite, leucocratic granite, garnet-biotite-quartz-feldspargneiss, monzogranite, migmatite.

Colour: Not mentioned in literature.

Veins, Pegmatites, Aplites, Greisens: None mentioned in literature.

Distinctive mineralogical characteristics:

Pa, Pac and Pag (NORSEMAN1) are part of the Mount Andrew Migmatite Complex, which isa migmatitic complex of gneisses and granitic material. The gneisses are predominantly felsicin composition, although some mafic lenses of amphibolite and granulite are present. Thegneiss is normally a biotite-quartz-feldspar rock, with or without garnets. Muscovite was notedat one locality. Mineral and grain size banding of the gneiss varies from millimeter to meterscale.

Veins, pods, dykes and sheets of leucocratic granitic material cut the gneisses. This graniticmaterial is characteristically equigranular and contains accessory magnetite. The largergranitic bodies also contain accessory chlorite or biotite. The grain size of the granitic rocksvaries from fine grained to very coarse grained. This variation often occurs within a singlebody. The banding is parallel to the length of the bodies.

The granitic rock typically intrudes the gneisses lit-par-lit. Although in some outcrops thegranitic bands intruded after the gneiss was folded, they are themselves usually folded.

^ab (NORSEMAN) is also part of the Mount Andrew Migmatite Complex, and is a garnet-biotite-quartz-feldspar augen gneiss probably derived from a metamorphosed porphyriticgranite.

^b (ZANTHUS). Note that this unit is distinguished as ^b_Z in this project’s GIS. It is agarnet-biotite-quartz-feldspar gneiss containing feldspar augen. It appears to be ametamorphosed porphyritic granite which could be comagmatic with rapakivi granite at themargin of the Fraser Complex.

pCg (ZANTHUS). Note that this unit is distinguished as pCg_Z in this project’s GIS.Undifferentiated granite and gneiss.

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BIRANUP SUPERSUITE

1 Capitalised map names denote 1:250 000 Sheet names

pCm (ZANTHUS). Note that this unit is distinguished as pCm_Z in this project’s GIS.Equigranular leucocratic granite intrusive into biotite granites; possibly ^y_Z intrusive intoArchaean granites.

pCn (ESPERANCE) comprises banded garnet, biotite gneiss and granitic rocks of varyingcomposition.

^g (CUNDEELEE) is granitic and migmatitic rocks, sheared and foliated granitic rocks,banded migmatite, gneiss, quartz-muscovite schist.

^l (ZANTHUS). Note that this unit is distinguished as ^l_Z in this project’s GIS. Porphyriticbiotite granite. Part of a Rb-Sr 1660 ± 40 My isochron (Arriens and Lambert 1969).

^m (BALLADONIA). Note that this unit is distinguished as ^m1 in this project’s GIS.Complex of leucocratic equigranular granitic material, gneisses and basic enclaves. Normally a biotite-quartz-feldspar rock with or without garnet.

^m (CUNDEELEE). Note that this unit is distinguished as ^m2 in this project’s GIS.Paragneiss and migmatite. The migmatite is a mixture of granitic gneiss, biotite-garnet gneissand coarse-grained quartz-feldspar rock. Biotite-rich zones between the palaeosome andneosome suggest that the felsic bands may have sweated out of the surrounding palaeosome.

^mm (RAVENSTHORPE) are migmatites mostly of oligoclase monzogranite to granodiorite.There is a general northward increase in metamorphic grade. In places the migmatitescommonly contain garnet and/or orthopyroxene.

^y (ZANTHUS). Note that this unit is distinguished as ̂ y_Z in this project’s GIS. It consists ofequigranular leucocratic granite with accessory biotite.

Breccias: None mentioned in literature.

Alteration in the granite: None mentioned in literature.

2.8 Extrusives None.

2.9 CountryRock

Contact metamorphism: None mentioned in literature.

Reaction with country rock: None mentioned in literature.

Units the granite intrudes: These granites intrude metasedimentary and meta-igneousgneisses of both Archaean and Proterozoic age.

Dominant rock types: Quartz-feldspar-biotite(-garnet) gneiss, granite gneiss, augen gneiss,granulite.

Potential hosts: None.

2.10 Mineralisation None.

2.11 GeochemicalData

Data source: Samples were collected by the GSWA.

Data quality: Good quality.

Are the data representative? The available data are very limited, and therefore potentially notrepresentative.

Are the data adequate? Because there is a possibility that the data is are representative, it isconsidered that the data are not adequate.

SiO2 range (Fig. 2.1): From 64 wt% to 77 wt%. The literature suggests that the Supersuite isdominated by felsic rocks.

Alteration (Fig. 2.2): There is some evidence of uranium loss, probably due to metamorphismor deformation.

• SiO2: None evident.• K2O/Na2O: No alteration obvious.• Th/U: Several samples are anomalously high, two are low.

© Geoscience Australia 2001 Albany-Fraser Province 2.3

BIRANUP SUPERSUITE

• Fe2O3/(FeO+Fe2O3): One sample is more reduced than the others.

Fractionation Plots (Fig 2.3): These granites are not fractionated.

• Rb: Values are low, increasing slightly with increasing SiO2.• U: Most values are very low (as indicated by the Th/U plot); one value is somewhat higher.• Y: Most values are low to moderate, increasing with increasing SiO2; two values are

(anomalously) low.• P2O5: Samples decrease with increasing SiO2, from low to very low.• Th: Values are very low to low, increasing slightly with increasing SiO2.• K/Rb: There is some scatter; values are moderate to moderately high. There may be an

increasing trend with increasing SiO2.• Rb-Ba-Sr: Most samples plot in the anomalous granite field; two plot in the granite field.• Sr: Values range from moderate to low, decreasing with increasing SiO2.• Rb/Sr: Values are very low, increasing very slightly in the most felsic samples.• Ba: Values range from high to moderately low, with considerable scatter.• F: No data.

Metals (Fig. 2.4):

• Cu: All values are low.• Pb: Ranges from low to moderately low, increasing slightly with increasing SiO2.• Zn: Ranges from moderate to low, decreasing with increasing SiO2.• Sn: No data.

High field strength elements (Fig. 2.5):

• Zr: Values range from moderate to low, decreasing with increasing SiO2.• Nb: All values are low.• Ce: Ranges from moderate to low with considerable scatter.

Classification (Fig. 2.6):

• The CaO/Na2O/K2O plot of White, quoted in Sheraton and Simons (1992): Plots in thegranite, monzogranite and granodiorite fields (one is in the trondhjemite field, but this ismost likely due to alteration).

• Zr/Y vs Sr/Sr*: Insuffiecient data.• Spidergram: Five of the samples are Sr-depleted, Y-undepleted; two are Sr-undepleted,

Y-depleted.• Oxidation plot of Champion and Heinemann (1994): Mostly oxidised - one sample is

reduced (probably due to alteration).• ASI: All samples are metaluminous or mildly peraluminous, ie are I-type.• A-type plot of Eby (1990): Plots within the normal range for Australian Proterozoic

granites (ie within and just above the range of Palaeozoic granites).

Granite type (Chappell and White 1974; Chappell and Stephens 1988): I-(granodiorite).

Australian Proterozoic granite type: Kalkadoon type - unmineralised, restite-dominated.

© Geoscience Australia 2001 Albany-Fraser Province 2.4

BIRANUP SUPERSUITE

Fig ure 2.1: His to gram of SiO2 val ues.

2.12 GeophysicalSignature

Radiometrics (Fig. 2.7): Potassium is slightly higher, thorium is slightly lower, and uranium issignificantly lower. Therefore the predicted RGB colour is red.

Gravity: Insufficient detail.

Magnetics: Insufficient detail.

2.13 References Arriens, P.A. and Lambert, I.B. 1969. On the age and strontium isotopic geochemistry ofgranulite-facies rocks from the Fraser Range, Western Australia, and the Musgrave Ranges,Central Australia, Geological Society of Australia, Special Publication number 2, 377-388.

Bunting, J.A., Van de Graaff, W.J.E. 1977. Cundeelee, Western Australia, 1:250 000Geological Series, Geological Survey of Western Australia, Explanatory Notes, SH/51-11,40pp.

Doepel, J.J.G. 1973. Norseman, Western Australia, 1:250 000 Geological Series, GeologicalSurvey of Western Australia, Explanatory Notes, SI/51-02, 40pp.

Doepel, J.J.G. and Lowry, D.C. 1970. Balladonia, Western Australia, 1:250 000 GeologicalSeries, Geological Survey of Western Australia, Explanatory Notes, SI/51-03, 19pp.

Doepel, J.J.G. and Lowry, D.C. 1970. Zanthus, Western Australia, 1:250 000 GeologicalSeries, Geological Survey of Western Australia, Explanatory Notes, SH/51-15, 19pp.

Lowry, D.C. and Doepel, J.J.G. 1974. Malcolm - Cape Arid, Western Australia, 1:250 000Geological Series, Geological Survey of Western Australia, Explanatory Notes, SI/57-07, 16pp.

Morgan, K.H. and Peers, R. 1973. Esperance - Mondrain Island, Western Australia, 1:250 000Geological Series, Geological Survey of Western Australia, Explanatory Notes, SI/51-06, 21pp.

Myers, J.S. 1990. Albany-Fraser Orogen, Western Australia Geological Survey, Geology andMineral Resources of Western Australia, Memoir 3, 255-263.

Nelson, D.R. 1995. Compilation of SHRIMP U-Pb zircon geochronology data, 1994,Geological Survey of Western Australia, Record 1995/3.

Thom, R., Lipple, S.L. and Sanders, C.C. 1977. Ravensthorpe, Western Australia, 1:250 000Geological Series, Geological Survey of Western Australia, Explanatory Notes, SI/51-05, 40pp.

© Geoscience Australia 2001 Albany-Fraser Province 2.5

BIRANUP SUPERSUITE

© Geoscience Australia 2001 Albany-Fraser Province 2.6

BIRANUP SUPERSUITE

2.2A: Na2O vs K2O

2.2B: Th/U vs SiO2

2.2C: Fe2O3/(FeO+Fe2O3)

Legend

© Geoscience Australia 2001 Albany-Fraser Province 2.7

BIRANUP SUPERSUITE

2.3A: Rb vs SiO2

2.3B: U vs SiO2

2.3C: Y vs SiO2

Legend

© Geoscience Australia 2001 Albany-Fraser Province 2.8

BIRANUP SUPERSUITE

2.3D: P2O5 vs SiO2

2.3E: Th vs SiO2

2.3F: K/Rb vs SiO2

Legend

© Geoscience Australia 2001 Albany-Fraser Province 2.9

BIRANUP SUPERSUITE

2.3G: Rb- Ba- Sr

Stronglydif fer en ti atedgran ite

Gran ite

To nal iteMon zo gran ite

Anoma lousgran ite

2.3H: Sr vs SiO2

2.3I: Rb/Sr vs SiO2

Legend

© Geoscience Australia 2001 Albany-Fraser Province 2.10

BIRANUP SUPERSUITE

2.3J: Ba vs SiO2

2.4A: Cu vs SiO2

NO FLUORINE DATA AVAILABLE

Legend

© Geoscience Australia 2001 Albany-Fraser Province 2.11

BIRANUP SUPERSUITE

2.4B: Pb vs SiO2

2.4C: Zn vs SiO2

Legend

NO TIN DATA AVAILABLE

© Geoscience Australia 2001 Albany-Fraser Province 2.12

BIRANUP SUPERSUITE

2.5A: Zr vs SiO2

2.5B: Nb vs SiO2

2.5C: Ce vs SiO2

Legend

© Geoscience Australia 2001 Albany-Fraser Province 2.13

BIRANUP SUPERSUITE

2.6A: CaO- Na2O-K2O

To nal ite

Gra no dio rite

Mon zo gran ite

Trondh jemite Gran ite

IN SUF FI CIENT DATA FOR Sr/Sr*

2.6C: Spider gramSiO2 range: 64- 77 wt%

Legend

© Geoscience Australia 2001 Albany-Fraser Province 2.14

BIRANUP SUPERSUITE

2.6D: Re dox plot

Strongly oxi dised

Oxi dised

Re duced

Strongly Re duced

2.6E: ASI vs SiO2

2.6F: Ga/Al vs HFSE (Eby, 1990)

Legend

© Geoscience Australia 2001 Albany-Fraser Province 2.15

BIRANUP SUPERSUITE

2.7A: K2O%Box- whisker

2.7B: Th ppmBox- whisker

2.7C: U ppmBox- whisker

Pro tero zoic me dian

Pro tero zoic me dian

Legend

Pro tero zoic me dian

Biranup Supersuite

MEANS AND STANDARD DEVIATIONS

Element Mean Median Standard Minimum Maximum Number ofDeviation Items

SiO2 71.67 73.5 4.81 64.1 76.8 7TiO2 0.45 0.23 0.33 0.15 0.85 7Al2O3 13.74 13.9 1.37 11.5 15.7 7Fe2O3 1.11 0.77 0.77 0.44 2.49 7FeO 1.87 1.06 1.44 0.63 4.43 7MnO 0.06 0.05 0.04 05 0.11 7MgO 0.75 0.62 0.52 0.15 1.45 7CaO 2.34 2.17 1.19 0.99 3.97 7Na2O 3.3 3.05 0.77 2.51 4.43 7K2O 4.03 4.07 1.08 2.62 5.21 7P2O5 0.1 0.05 0.1 05 0.25 7H2O+ 0.34 0.34 0.11 0.21 0.52 6H2O- 0.08 0.08 0.04 10 0.13 6CO2 0.05 0.04 0.04 02 0.1 6Ba 1208 1068 507.81 656 1938 7Rb 118.86 113 48.71 44 185 7Sr 254 269 135.84 73 406 7Pb 23.86 24 5.52 16 32 7Th 13.43 14 8.14 23 7U 3.29 4.86 14 7Zr 227.57 246 107.67 109 366 7Nb 6.79 7 3.4 11 7Y 29.14 33 16.18 6 49 7La 62 45 49.54 9 153 7Ce 114.43 100 86.14 17 274 7V 30.57 28 24.61 65 7Cr 13.71 7 14.27 37 7Ni 5.93 5 4.76 13 7Cu 9.14 7 4.88 15 7Zn 47.14 50 22.2 20 76 7Ga 14 14 2.08 12 17 7

© Geoscience Australia 2001 Albany-Fraser Province 2.16

BIRANUP SUPERSUITE

3 NORNALUP Supersuite

3.1 Timing 1300 - 1180 Ma

3.2 IndividualAges

Primary Ages:

1. Hornblende- biotite sye no gran ite gneiss, Co ra mup Hill Quarry[1]

1283 ± 13 Ma, SHRIMP2. Bio tite mon zo gran ite gneiss, Mount Bur dett[1]

1299 ± 18 Ma, SHRIMP3. Re crys tal lised leu co gran ite, Ob ser va tory Point[1]

1288 ± 12 Ma, SHRIMP4. Biotite- hornblende mon zo gran ite gneiss, Poi son Creek[1]

1330 ± 14 Ma, SHRIMP5. En der bitic gneiss, Al bany[2] 1289 ± 10 Ma, SHRIMP6. Por phy ritic bio tite mon zo gran ite, Es perance Har bour jetty[1]

1138 ± 38 Ma, SHRIMP7. Por phy ritic bio tite gran ite, Bal la do nia Rock[1]

(con tains in heri tance of 1285 ± 57 Ma) 1135 ± 56 Ma, SHRIMP8. Mount Frank lin gran ite[3] 1189 ± 9 Ma, SHRIMP9. Aplite dyke, Poron gu rups[3] 1194 ± 16 Ma, SHRIMP10. Poron gu rups Gran ite[3] 1184 ± 11 Ma, SHRIMP11. Al bany Ada mel lite[2] 1174 ± 12 Ma, SHRIMP12. Mon zo gran ite - Mt Cha da lup[2] 1177 ± 4 Ma, SHRIMP

Sources: [1] Nel son (1995), [2] Pidgeon (1990), [3] Black et al.(1992).

The above samples correspond to the following map unit symbols on the 1:250 000 geologicalmap series:

1. pCn - Esperance; 2, 3, 6. pCm - Esperance; 4. Pb - Malcolm; 5. Pna - Mount Barker; 7. Pl -Balladonia; 8. Pgp - Pemberton; 9, 10, 11. Pgp - Mount Barker; 12. Pge - Pemberton.

3.3 RegionalSetting

Granites intruded syn- and post-deformation at around 1300 Ma and 1190 Ma in thesouthern part of the Albany Mobile belt. They intruded metasediments and meta-igneous rocks, which were strongly deformed and metamorphosed as part of the sameevent in which the granites were emplaced.

3.4 Summary These granites are extensive, but are unfractionated and restite-dominated. They covera broad compositional range, but are dominated by biotite granite, porphryritic graniteand monzogranite. It is difficult to assign the granites into the two age groups present,due to the scarcity of geochronological and geochemical data, and also due to thereconnaissance nature of mapping covering the area.

3.5 Potential This Supersuite is unfractionated and in places xenolith-bearing. It is not thought tohave any significant mineralisation potential.

Cu: LowAu: LowPb/Zn: LowSn: LowMo/W: LowCon fi dence level: 110

© Geoscience Australia 2001 Albany-Fraser Province 3.1

3.6 DescriptiveData

Location: Eastern and western Albany-Fraser Block.

Dimensions and area: Granites in the eastern part of the Albany-Fraser block crop out over alength of about 200 km and a width of 100 km, in a northeasterly direction. They have a mappedoutcrop area of ~35,000 km2. In the western part of the province, they extend in an east-westdirection over 200 km, with a width of 70 km. They have a mapped outcrop area of ~46,000km2.

3.7 Intrusives Component plutons: Below is a table of granites as they appear on the 1:250 000 geologicalmap sheets. Many of the granites have been included in the informally named BurnsideSupersuite in the western half of the Block. Some of the granites have been informally named,but these names have not been used in this report, as it is easier to make spatial reference back tothe published maps by using mapsymbols. Note that these are the map symbols used on thepublished maps; the symbols used in this project’s GIS are slightly different in some cases inorder to differentiate those units. Where different symbols have been used, they are noted in theunit’s mineralogical descriptions below.

SYMBOL DESCRIPTION MAPS

^b Gnt-bi-qtz-feld gneiss containing feldspar augenMalcolm,Balladonia

^bi Inferred augen gneiss Malcolm

^cGranite and gneiss - not subdivided on map, and includesunassigned metamorphic and igneous rocks on islands

Balladonia,Mt Barker

pC Undetermined Precambrian rocks Esperance

pCgCoarse even-grained & porphyritic granite with pink feldsparlaths

Esperance

pCm Migmatite - lath granite and garnet gneiss Esperance

pCn Gneiss - banded gnt-bi gneiss + granitic rocks Esperance

^ga Augen gneiss; developed from Pgp Mt Barker

^gc Coarse even-grained granodiorite, monzogranite and granite Pemberton

^ge Medium even-grained biotite monzograniteMt Barker,Pemberton

^gm Mixed granitic rocks; mostly porphyritic and even-grained Mt Barker,Pemberton

^gp Porphyritic biotite granite and monzograniteMt Barker,Pemberton

^gv Fine to medium-grained monzogranite and granite Pemberton

^k Gneissic monzogranite - fine-grained Balladonia

^l Biotite granite, K-spar phenocrysts in placesMalcolm,Balladonia

^li Inferred biotite granite Malcolm

^m Migmatite Pemberton

^m Mixed granitic rocks Malcolm

^mi Inferred mixed granitic rocks Malcolm

^nMigmatite of granitic rocks, amphibolite, basic granulite,quartzite

Malcolm

^na Augen gneiss; coarse-grained with microcline augen Mt Barker

^nb Quartz-feldspar-biotite gneiss Mt Barker

^nd Deformed granitic orthogneiss Pemberton

^ng Granitic gneiss Mt Barker

^ni Inferred migmatite Malcolm

^nsGneiss; granoblastic granite, monzogranite; streaks of maficmins

Mt Barker

^sa Felsite Malcolm

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^y Equigranular leucocratic graniteMalcolm,Balladonia

^yi Inferred equigranular leucocratic granite Malcolm

Form: Commonly well exposed as domes. Also well exposed along the coast.

Metamorphism and Deformation: These granites are variably deformed and metamorphosed.They were emplaced over a relatively broad period of time, both syn- and post-tectonically.

Dominant intrusive rock types: Granite, monzogranite, porphyritic granite, gneiss.

Colour: Pink to pale grey.

Veins, Pegmatites, Aplites, Greisens: Biotite-rich schlieren at Wylie Head (Esperance) is partof pCg, and pegmatite is found at the same locality.

Distinctive mineralogical characteristics: (By map symbol with 1:250 000 map sheet namethat unit occurs on in brackets)

^b and ̂ bi (Malcolm, Balladonia): Garnet-biotite-quartz-feldspar gneiss containing feldsparaugen. Probably formed by the metamorphism of a porphyritic granite.

pC (Esperance) are undetermined Precambrian rocks mapped by photo interpretation.

Pc (Balladonia) is undivided granite and gneiss.

pCg (Esperance) is a coarse, even-grained to porphyritic, pink lath feldspar granite. It is pink topale grey, with abundant black biotite. The predominant minerals are microcline, plagioclase,quartz and biotite, with lesser muscovite, apatite, zircon, fresh black opaque grains and titanite.Microcline phenocrysts are up to 3 cm long. Alteration is limited to light kaolinisation. Minoralteration (of plagioclase) to sericite and carbonate has occurred.

pCm (Esperance) is migmatite - alternating bands and mixed rock composed of lath granite andgarnet gneiss in varying proportions, ie is a mixture of intruded granite and gneissic countryrock. The rock is very broadly but distinctly banded in a mixture of dark and light rock ofvarying grain sizes, comprising a metamorphic phase of granitic gneiss, mafic palaeosomelayers, amphibole-rich layers, granite of the neosome phase, and pegmatoid leucosomes. Thepredominant minerals of the granitic gneiss are quartz, microcline and plagioclase, with biotiteand accessory minerals including zircon, fresh black opaque grains, garnet, titanite and apatite.The mafic palaeosome layers are characterised by an abundance of biotite, or biotite andamphibole and the predominance of plagioclase over microcline. In one specimen the biotite ispartly altered to chlorite which includes a trace of fluorite. Accessory minerals include freshblack opaque grains, titanite and apatite. The amphibole-rich layers are composed of freshplagioclase, microperthitic microcline, quartz, amphibole and biotite, and accessories includezircon, apatite, large grains of an opaque mineral rimmed by titanite, anhedral grains of yellowtitanite, and apatite. The typical granite of the neosome phase is a medium-grained, dark pink,porphyritic biotite granite. Quartz, microcline, plagioclase and biotite are the predominantminerals, with accessory opaques altering to leucoxene, apatite, zircon and rare pyrite, titaniteand allanite. The pegmatoid leucosomes are composed of a coarse-grained aggregate of quartz,microperthitic microcline and sericitised plagioclase, with traces of biotite, muscovite, opaquegrains, zircon, amphibole and carbonate.

pCn (ESPERANCE) Gneissic migmatite - banded, garnet-biotite gneiss and granitic rocks ofvarying composition and texture, including granite, amphibolite, augen gneiss, pegmatite andmetamorphosed dolerite.

^ga (Mount Barker) includes ^ge, and ^gp which developed zones of augen gneissaccompanied by garnet.

^gc (Pemberton) is a coarse, even-grained granitic rock ranging from granodiorite to granitecontaining unaligned and tabular microcline similar in size to the other felsic minerals.

^ge (Pemberton, Mount Barker) is a fine to medium-grained, even-grained granodiorite togranite. Contains microcline and hornblende.

^gm (Pemberton) are mixed granitic rocks of ^ge, ^gp and ^gc in varying proportions.

^gp (Mount Barker, Pemberton) is a megacrystic monzogranite, and is the main rock type inthe Albany area. The usual mineral assemblage is quartz, microcline, oligoclase/ andesine, andaccessory biotite, opaque grains and apatite. Hornblende is a distinctive accessory mineral

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restricted for the most part to the Porongurup Pluton, parts of the Albany Adamellite and thegranitoid north of Point Hillier. Textures range from undeformed allotriomorphic granular with alignment of tabular microcline megacrysts to granoblastic or gneissic granitoid with afoliation/lineation of quartz, feldspar and biotite-feldspar augen. Megacrysts typicallyconstitute 60% of the rock and are strongly aligned. Xenoliths in the granitoids includeamphibolite, quartzite, granoblastic granitoid, gneiss, and mafic granulite. Most of theseinclusions can be related to the adjacent gneissic terrain.

^gv (Pemberton) is a fine to medium-grained monzogranite with scattered microclinemegacrysts, compositionally and texturally similar to ^ge except for the development of themicrocline megacrysts.

^k (Balladonia) is an isolated outcrop of fine-grained, well foliated (gneissic) monzogranite.

^l and ^li (Malcolm, Balladonia): Granite - generally with K-feldspar phenocrysts; biotitegranite in part porphyritic on Malcolm.

^m and ̂ mi (Malcolm) - designated as ̂ m3 in this project’s GIS: Mixed granitic rocks. Someoutcrops within this belt are of a single rock type and others are of a migmatite of more than onegranitic rock. For instance, at and to the south of Point Jedacorrudup, unfolded pegmatites andfine to medium-grained leucocratic granite intrude strongly foliated medium-grained graniteand augen gneiss. Strongly foliated dykes of intermediate rock also appear to intrude the gneiss. To the north and east of Mount Baring are outcrops of foliated fine-grained biotitic granitic rock and gneiss. These are intruded by numerous aplites, pegmatites and quartz veins.

^m (Pemberton) - designated as ^m in this project’s GIS: Migmatite - nebulitic or withstrongly contorted banding. Palaeosome often a streaked-out augen gneiss.

^n and ^ni (Malcolm) is a migmatite of granitic rocks, amphibolite, mafic granulite andquartzite.

^na is augen gneiss on both Pemberton and Mount Barker mapsheets. On Pemberton it is acoarse-grained augen gneiss and is the result of cataclastic deformation of porphyritic granite.On Mount Barker it ranges from a medium to coarse, even-grained, granoblastic rock with clotsof biotite to a rock with ‘megacrysts’ of microcline or patches of coarse-grained quartz-microcline-plagioclase in a finer-grained matrix. Typical examples consist of quartz,microcline, plagioclase (antiperthitic) and red-brown biotite, and have the bulk composition ofan monzogranite. Clark (1995) divided this unit in the area immediately around Albany intomonzogranitic gneisses and enderbitic gneisses.

^nb (Mount Barker) is quartz-feldspar-biotite (-garnet-hypersthene) gneiss; compositionallylayered gneiss with subordinate Pns and granofels; includes amphibolite and mafic granulitelayers; granoblastic fabric.

^nd (Pemberton) is an intensely deformed granitic orthogneiss characterised by large,compound quartzofeldspathic augen. The parent rock is not identified but was presumably aporphyritic or coarse-grained granite.

^ng (Mount Barker) is a pale-grey, fine to medium-grained, leucocratic granite gneiss with agranoblastic texture. It has the composition of monzogranite and consists of quartz, microclineand oligoclase, with very small amounts of biotite and goethite pseudomorphs after garnet.

^ns (Mount Barker) is gneiss; granoblastic granite, monzogranite with streaks of maficminerals (biotite, hornblende or pyroxene) or magnetite, garnet common; includes minorlayered and granofelsic rocks.

^sa (Malcolm): Quartz-feldspar porphyry. It contains flakes of biotite aligned parallel to thestrike of the underlying sediments. It is not known whether this is a metamorphic or flowalignment, or whether the rock is a flow or a sill.

^y and ^yi (Malcolm, Balladonia): Even-grained leucocratic granite.

Breccias: None reported in literature.

Alteration in the granite: Only minor sericitisation and/or kaolinisation are reported in a fewgranites.

3.8 Extrusives None reported in literature.

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3.9 CountryRock

Contact metamorphism: None reported in literature.

Reaction with country rock: None reported in literature.

Units the granite intrudes: These granites intrude metasedimentary and meta-igneousgneisses of both Archaean and Proterozoic age.

Dominant rock types: Quartz-feldspar-biotite(-garnet) gneiss, granite gneiss, augen gneiss,granulite.

Potential hosts: None.

3.10 Mineralisation None known.

3.11 GeochemicalData

Data source: Samples were collected by Curtin University of Technology Honours students (I.Gregory, W. Clark and J. Pope [dec.]), and GSWA workers.

Data quality: Good, as samples were analysed either at AGSO (Curtin students) or GSWA.

Are the data representative? Probably.

Are the data adequate? Yes.

SiO2 range: Silica ranges from 50 wt% to 79 wt%.

Alteration (Fig. 3.2): Many samples have an anomalously high Th/U ratio, indicating thatsome alteration (most likely due to deformation) has taken place. Some samples may besericitised.

• SiO2: No silica alteration is obvious.• K2O/Na2O: Most samples are unaltered, except for some which have lost sodium and

possibly potassium (this possibly indicates sericitisation).• Th/U: Many samples have a high ratio, indicating uranium loss.• Fe2O3/(FeO+Fe2O3): Most samples are reduced, and appear unaltered.

Fractionation Plots (Fig. 3.3): The granites are unfractionated. The presence of xenolithssuggests that the granites are restite-dominated.

• Rb: Values are low to medium, and do not show a trend.• U: All values are low.• Y: Values range from very low to high, and are quite scattered.• P2O5: Values range from moderately high to very low, decreasing strongly with

increasing SiO2.• Th: Values range from very low to moderately high, and show considerable scatter.• K/Rb: Values range from low to very high, and show an increasing trend with increasing

SiO2 but with some scatter.• Rb-Ba-Sr: Most samples plot in the granite or anomalous granite fields.• Sr: Values range from moderate to low, and decrease slightly with increasing SiO2.• Rb/Sr: All values are very low.• Ba: Values range from low to very high, with a lot of scatter.• F: No data available.

Metals (Fig. 3.4):

• Cu: Values range from high to very low, decreasing with increasing SiO2.• Pb: Values range from low to moderately high, increasing with increasing SiO2.• Zn: Values range from high to very low, decreasing with increasing SiO2.• Sn: Values are low to very low.

High field strength elements (Fig. 3.5):

• Zr: Values range from moderate to low. The trend increases up to about 68 wt%, thendecreases with increasing SiO2.

• Nb: Values range from moderate to very low. The trend increases up to about 68 wt%, then decreases with increasing SiO2.

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• Ce: Values range from very high to very low. The trend increases up to about 68 wt%, thendecreases with increasing SiO2, although there is considerable scatter.

Classification (Fig. 3.6):

• The CaO/Na2O/K2O plot of White, quoted in Sheraton and Simons (1992): Most of thesamples are monzogranites or granites, with some granodiorites.

• Zr/Y vs Sr/Sr*: The samples plot near the Zr/Y axis, showing that they are strongly Sr-depleted.

• Spidergram: The granites are Sr-depleted, Y-undepleted, and are also very low in Nb.• Oxidation plot of Champion and Heinemann (1994): Most of the samples are reduced,

with the rest being oxidised. All are close to the reduced-oxidised boundary.• ASI: Most of the samples are metaluminous, becoming more peraluminous with

increasing SiO2. This is a good I-type trend.• A-type plot of Eby (1990): Most of the samples appear to be normal for Australian

Proterozoic granites.

Granite type (Chappell and White 1974; Chappell and Stephens 1988): I-(granodiorite).

Australian Proterozoic granite type: Kalkadoon type - unmineralised, restite-dominated.

3.12 GeophysicalSignature

Radiometrics (Fig. 3.7): Potassium is well above the Proterozoic median, Th is slightly above,and U is below. The predicted RGB colour therefore is orange.

Gravity: Insufficient detail.

Magnetics: Insufficient detail.

3.13 References Black, L.P., Harris, L.B. and Delor, C.P. 1992. Reworking of Archaean and Early Proterozoiccomponents during a progressive, Middle Proterozoic tectonothermal event in the AlbanyMobile Belt, Western Australia, Precambrian Research, 59, 95-123.

Clark, W.C. 1995. Granite petrogenesis, metamorphism and geochronology of the westernAlbany-Fraser Orogen, Albany, Western Australia, B.Sc. (Hons) thesis, Curtin University ofTechnology, Perth, Australia, unpublished.

Doepel, J.J.G. and Lowry, D.C. 1970. Balladonia, Western Australia, 1:250 000 GeologicalSeries, Geological Survey of Western Australia, Explanatory Notes, SI/51-03, 19pp.

Gregory, I. 1995. The emplacement and deformation of two granitoids in the Denmark regionof the Albany Mobile Belt, Western Australia, B.Sc. (Hons) thesis, Curtin University ofTechnology, Perth, Australia, unpublished.

Lowry, D.C. and Doepel, J.J.G. 1974. Malcolm - Cape Arid, Western Australia, 1:250 000Geological Series, Geological Survey of Western Australia, Explanatory Notes, SI/57-07, 11,16pp.

Morgan, K.H. and Peers, R. 1973. Esperance - Mondrain Island, Western Australia, 1:250 000Geological Series, Geological Survey of Western Australia, Explanatory Notes, 21pp.

Muhling, P.C. and Brakel, A.T. 1985. Mount Barker - Albany, Western Australia, 1:250 000Geological Series, Geological Survey of Western Australia, Explanatory Notes, 21pp.

Nelson, D.R. 1995. Compilation of SHRIMP U-Pb zircon geochronology data 1994,Geological Survey of Western Australia, Record 1995/3.

Pidgeon, R.T. 1990. Timing of plutonism in the Proterozoic Albany Mobile Belt, southwesternAustralia, Precambrian Research, 47, 157-167.

Wilde, S.A. and Walker, I.W. 1984. Pemberton - Irwin Inlet, Western Australia, 1:250 000Geological Series, Geological Survey of Western Australia, Explanatory Notes, 37pp.

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Legend

3.2A: Na2O vs K2O

3.2B: Th/U vs SiO2

3.2C: Fe2O3/(FeO+Fe2O3)

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3.3A: Rb vs SiO2

3.3B: U vs SiO2

3.3C: Y vs SiO2

Legend

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3.3D: P2O5 vs SiO2

3.3E: Th vs SiO2

3.3F: K/Rb vs SiO2

Legend

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3.3G: Rb- Ba- Sr

Stronglydif fer en ti atedgran ite

Gran ite

To nal iteMon zo gran ite

Anoma lousgran ite

3.3H: Sr vs SiO2

3.3I: Rb/Sr vs SiO2

Legend

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3.3J: Ba vs SiO2

3.4A: Cu vs SiO2

NO FLUORINE DATA AVAILABLE

Legend

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3.4B: Pb vs SiO2

3.4C: Zn vs SiO2

3.4D: Sn vs SiO2

Legend

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3.5A: Zr vs SiO2

3.5B: Nb vs SiO2

3.5C: Ce vs SiO2

Legend

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3.6A: CaO- Na2O-K2O

To nal ite

Gra no dio rite

Mon zo gran ite

Trondh jemite Gran ite

3.6B: Zr/Y vs Sr/Sr*

3.6C: Spider gramSiO2 range: 48- 77%

Legend

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3.6D: Re dox plot

Strongly oxi dised

Oxi dised

Re duced

Strongly Re duced

3.6E: ASI vs SiO2

3.6F: Ga/Al vs HFSE (Eby 1990)

Legend

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3.7A: K2O%Box- whisker

3.7B: Th ppmBox- whisker

3.7C: U ppmBox- whisker

Pro tero zoic me dian

Pro tero zoic me dian

Legend

Pro tero zoic me dian

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MEANS AND STANDARD DEVIATIONS

Element Mean Median Standard Minimum Maximum Number ofDeviation Items

SiO2 68.48 70 5.41 49.74 78.99 81TiO2 0.59 0.46 0.42 0.03 3.05 81Al2O3 14.03 14.25 1.51 5.81 17.07 81Fe2O3 1.03 0.87 0.71 06 4.88 81FeO 3.41 2.57 3.15 0.22 24.86 81MnO 0.08 0.06 0.08 05 0.54 80MgO 1.09 0.78 1.21 0.04 8.87 81CaO 2.42 1.97 1.3 0.57 6.33 81Na2O 2.84 2.9 0.67 0.36 4.42 81K2O 4.53 4.89 1.35 1.28 6.38 81P2O5 0.18 0.14 0.14 0.01 0.82 79H2O+ 0.53 0.53 0.25 0.25 0.82 4H2O- 0.12 0.13 0.05 10 0.15 4CO2 0.09 0.03 0.13 02 0.29 4LOI 1 0.95 0.37 0.31 2.2 77Ba 1230.41 1022 815.83 149 4544 81Li 34.75 31 25.66 2 187 77Rb 204.59 205 79.03 33 414 81Sr 211.88 175 203.72 22 1890 81Pb 36.05 36 11.49 11 73 81Th 35.38 23 26.15 3 99 81U 3.93 3 2.61 18 81Zr 269.4 263 151.81 14 1221 81Nb 19.17 16 13.64 101 81Y 37.53 31 34 1 234 81La 96.54 83.5 62.37 8 303 80Ce 189.19 170 123.97 10 616 81Pr 17.88 15 12.44 59 77Nd 71.64 59 48.85 251 77Sc 11.71 8 9.4 50 77V 42.49 27 38.16 186 81Cr 57.48 9 91.88 593 81Mn 745.86 609 606.56 30 4243 77Ni 9.82 3 32.77 290 81Cu 9.79 6 12.45 76 81Zn 74.63 62 65.11 2 554 81Sn 3.42 3 1.69 10 77Mo 1.03 0.16 2 77Ga 18.86 19 3.02 10 25 81As 0.79 0.61 5 77S 200.34 120 217.78 30 1242 77Cl 196.83 97.5 197.98 44 501 6Be 3.86 3 2.36 1 21 71Ag 2.32 2 0.7 1 5 77Bi 1.03 0.35 4 77Hf 7.82 7 5.41 41 77Ta 1.47 0.91 5 77Cs 5.31 4 5.13 32 76Ge 2.25 2 0.69 5 77Se 0.5 - 77

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